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Onondaga Limestone
Onondaga Limestone
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The Onondaga Limestone is a group of hard limestones and dolomites of Devonian age that forms geographic features in some areas in which it outcrops; in others, especially its Southern Ontario portion, the formation can be less prominent as a local surface feature.[citation needed][1]

Key Information

In upstate New York and the Niagara peninsula of southern Ontario the sedimentary rocks tend to dip downward in a generally southern direction. The Onondaga outcrops in a line that usually forms an escarpment (the steep face of a cuesta), because of its resistance to erosion. The outcrop can be traced from the Hudson River valley westward along the southern rim of the Mohawk River valley, passing just south of Syracuse, and along the northern heads of the major Finger Lakes to Buffalo, New York. From Fort Erie, Ontario westward it runs along the north shore of Lake Erie for about 85 km and continues in a west-northwest direction inland for another ~90 km to about Ingersoll and Woodstock, Ontario (as shown in the map on the right). To the west and north these rocks are known as the Amherstburg Formation of the Detroit River Group.[2] Northwest of Ingersoll and Woodstock, across the crest of the Algonquin Arch, the band of outcrop turns more northerly, and strikes north-northwest for about 140 km to the east shore of Lake Huron in the Kincardine area (as shown in the map on the right). These rocks continue northwestwards under Lake Huron, and reappear in the northern part of the southern peninsula of Michigan, north of Alpena[3] (as shown in the map on the right). To the west, its equivalent, the Detroit River Group,[3] outcrops near Detroit and Windsor just north of the Lake Erie shoreline (as shown in the map on the right). The Detroit River Group is not topographically distinct west of Windsor in Michigan, but is noticeable as a steep hill just northwest of Leamington.

Chittenango Falls

In several spots it is breached by geologically young streams and spectacular waterfalls are formed, such as at Chittenango Falls just east of Syracuse, Buttermilk Falls at Le Roy, New York and Indian Falls west of Batavia.

A few other breaches occur in older valleys, which likely once had waterfalls, but erosion eventually obliterated them. Such breaches occur at the Tully valley, the Genesee River valley near Avon, New York, and at Port Colborne, Ontario, where the old valley forms a harbor on Lake Erie.

The formation is broken by the only major fault line in western New York, the Linden Fault just east of Batavia, where the eastern side of the fault has dropped down and the ledge moved southward relative to the western side. On the western side of the fault in Genesee County the escarpment achieves its greatest prominence. The New York State Thruway has a rock cut at Batavia which clearly shows the fault and is a popular point for geology class field trips.[4] The fault, which runs from Attica, New York northward to Lake Ontario, is still active and periodically causes minor earthquakes in the area.

The Onondaga Limestone also can be found in other areas where rocks of the same age outcrop, such as in western Pennsylvania and Michigan but they do not form prominent geographic features.

A similar and more prominent outcrop known as the Niagara Escarpment runs parallel and about 25 miles (40 kilometers) to the north through upstate New York, and similarly curves northwestward in southern Ontario toward Lake Huron and eventually into Michigan's Upper Peninsula and Wisconsin's Door Peninsula.

Another smaller outcrop known as the Portage Escarpment lies about 35 miles (56 km) to the south, running along the southern ends of the Finger Lakes and forming Cascadilla, Ithaca and Buttermilk Falls in Ithaca.

The Onondaga Escarpment contains significant outcrops of flint (a type of chert) which bears the escarpment's name. This variety of chert was of great importance to First Nations peoples throughout Southern Ontario, who used it to make stone tools (lithics) such as projectile points and hide scrapers. This variety of chert, which is of reasonably high-quality and which was highly valued by First Nations peoples, is often a common variety of chert recovered archaeologically from sites relatively adjacent to outcrops; for example, Onondaga-variety chert comprises 95% of all of the flint material from some sites in Milton, Ontario. The material has also been found as well at some distance from its original source; Onondaga chert has been recovered at the late archaic Duck Lake archaeological site in northern Michigan,[5] circa 400 kilometers from the nearest outcropping of the material. This wide distribution implies either a very large seasonal migration of ancient peoples or long-distance trade routes, with both likely being the case at different times throughout the prehistory of the Great Lakes region.[6]

Description

[edit]
1884 label for Onondaga Limestone.

The Onondaga Limestone is composed of four main subunits. In descending order:[7]

  • Seneca Member
  • Moorehouse Member
  • Nedrow Member
  • Edgecliff Member

The Seneca and Moorehouse members are sharply divided by the Tioga-B Bentonite layer, which was formed in a very short time period as the result of a large volcanic eruption in what is now the state of Virginia.

Relative age dating of the Onondaga places its formation in the Eifelian to Givetian stage of the Middle Devonian period, or 391.9 to 383.7 Ma.[8] Radiometric dating of a sample from the bentonite at the top of the Onondaga placed it at 390 ± 0.5 Ma.[9] The formation is time equivalent with the Floresta Formation of the Altiplano Cundiboyacense, Colombia.[10]

Onondaga limestone dimension stone

[edit]

Onondaga limestone[7][11] was quarried as dimension stone for construction of limestone buildings.

The following buildings contain structural Onondaga limestone:

References

[edit]

Further reading

[edit]
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Onondaga Limestone

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The Onondaga Limestone is a prominent Middle geological formation, primarily consisting of light- to medium-gray, fine-grained, interbedded with chert nodules and lenses, deposited in shallow marine environments across the Appalachian Basin approximately 393 to 387 million years ago, primarily of Eifelian age, extending into the lower Givetian stage. Named for exposures in , where it was first described in 1839, the formation reaches thicknesses of 8 to 35 meters (25 to 110 feet) and forms a relatively tabular unit that thins toward basinward . Spanning over 550 kilometers from Buffalo to the region and southward to Port Jervis in New York, the Onondaga Limestone underlies about 40% of the state (roughly 50,535 square kilometers) and correlates with units such as the Needmore Formation in , , and , as well as the lower Columbus Limestone in . It overlies the Schoharie Grit or Oriskany Sandstone and is gradationally overlain by the Marcellus Shale, marking key stratigraphic boundaries in the Eifelian to lower Givetian stages. The formation's lithology includes members like the Edgecliff (bioclastic limestone), Nedrow (shaly limestone), and Moorehouse (cherty limestone), reflecting three third-order depositional sequences influenced by sea-level changes. Paleontologically significant for preserving the diverse Onondaga Fauna—a assemblage of including corals, brachiopods, trilobites, and —the formation provides insights into Middle and . Hydrologically, it functions as a major karstic in regions like eastern Erie and Niagara Counties, New York, with thicknesses of 25 to 110 feet and features such as sinkholes that influence . Historically, its durable stone has been quarried for building purposes, appearing in early 20th-century structures and even contributing chert to prehistoric tool-making by . As a datum plane in regional , the Onondaga Limestone remains essential for correlating rocks across the .

Geological Overview

Age and Depositional Environment

The Onondaga Limestone is dated to the Eifelian stage of the Middle period, spanning approximately 393 to 388 million years ago. This temporal placement aligns with radiometric constraints and biostratigraphic correlations within the timescale. The formation was deposited in a shallow, tropical marine environment on a carbonate platform in the northern Appalachian Basin, situated within about 10° of the during a period of relative tectonic stability. This setting formed part of an epicontinental sea influenced by early phases of the , which introduced initial clastic influxes from northern highlands and contributed to basin through thrust loading. Water depths ranged from shallow shelf conditions (less than 100 meters) in the northwest to deeper basinal areas exceeding 150 meters southeastward, supporting widespread carbonate accumulation. Deposition occurred as part of a transgressive-regressive within the broader megasequence, beginning with a transgression that promoted initial shallow-water buildup and progressing to deeper settings before a regressive phase terminated limestone accumulation with influx. Specific depositional included reefs and bioherms in high-energy zones, protected lagoons with finer-grained sediments, and open shelf environments characterized by crinoidal packstones and calcisiltites, ultimately yielding hard s and minor dolomites. These reflect third-order cycles of base-level change, with retrogradational parasequences during transgression and shallowing-upward trends in later stages. The is divided into members such as Edgecliff, Nedrow, Moorehouse, and Seneca, each recording shifts in water depth and energy.

Lithology and Stratigraphy

The Onondaga Limestone is predominantly composed of micritic and bioclastic limestones, exhibiting a range of depositional textures including grainstone, packstone, and wackestone. These textures reflect deposition in shallow marine environments, with micritic varieties dominated by fine-grained carbonate mud and bioclastic components consisting primarily of fossil fragments such as ossicles and shell debris bound by cement. Minor silica replacement occurs as chert nodules and layers, particularly in argillaceous intervals, while —irregular dissolution seams formed during pressure solution —are common, enhancing bedding-parallel compaction. In New York, the formation is divided into four main members, from base to top: Edgecliff, Nedrow, Moorehouse, and Seneca, reflecting a progression from reefal to more argillaceous . The lowermost Edgecliff Member consists of coral-rich, massive beds of crinoidal grainstone and packstone, often forming bioherms with coarse bioclastic textures and minimal chert. Overlying it, the Nedrow Member is transitional, featuring shaly, argillaceous limestones with scattered chert nodules and wackestone textures that become cleaner toward the east and west. The central Moorehouse Member is characterized by cherty, nodular limestones with fine-grained micritic textures, prominent , and local dolomitic intervals indicating episodes of marine salinization. The uppermost Seneca Member comprises argillaceous, often dolomitic limestones with wackestone to packstone fabrics, chert nodules, and , marking a gradual transition to overlying shales of the Hamilton Group. The formation's total thickness in New York typically ranges from 20 to 50 meters, though it can exceed 50 meters in some regions, with variations due to depositional changes and post-depositional dolomitization in upper members. Petrographically, the limestones are fine- to medium-crystalline with sparry cement filling intergranular pores, abundant fragments, and subordinate silica as replacement chert, contributing to the formation's resistance to .

Geographic Distribution

Primary Locations and Outcrops

The Onondaga Limestone has its type locality in Onondaga County, New York, where it forms prominent exposures that define the formation's characteristic lithology. Primary surface outcrops are widespread in central and eastern New York, particularly in the Finger Lakes region and areas such as Otsego County, where the limestone creates resistant escarpments and quarry sites. These exposures extend over a belt exceeding 550 kilometers, tracing from western New York through the Helderberg region and southward along the Hudson Valley. The formation's distribution continues beyond New York into neighboring regions, including to the south, and farther southeast, and southwestern Ontario, , where equivalent strata are recognized. Notable outcrops highlight its role in shaping regional topography; for instance, the Onondaga Escarpment in features the as a , forming a steep boundary between the Erie Plain and the Ontario Lowlands. Similarly, the Helderberg Escarpment west of Albany displays thick beds of the Onondaga, contributing to the area's dramatic cliffs and features. Along the Catskill Front, the outcrop belt curves southward near Catskill and Kingston, exposing the limestone in a series of folds and valleys that mark the transition to the . In these surface expressions, chert nodules within the limestone often weather out distinctly, aiding identification in the field. Subsurface, the Onondaga underlies extensive portions of the Appalachian Basin across the , serving as a key stratigraphic marker in drilling and basin analysis.

Variations in Thickness and Extent

The Onondaga Limestone displays notable variations in thickness across its depositional basin in New York State, generally ranging from about 20 meters to over 60 meters, with local reefal buildups exceeding 70 meters, particularly in south-central areas; the formation generally thickens southeastward due to depositional patterns and pre-depositional facies changes, as it transitions from carbonate-dominated environments in the central basin to more expansive settings toward the southeast. In central New York, typical thicknesses are around 25-35 meters, serving as a transitional zone between these variations. Laterally, the formation extends approximately 400 kilometers east-west across New York, from near in the west to the vicinity of Albany in the east, before pinching out against the emerging Acadian highlands, which limited further eastward carbonate deposition. This extent reflects the broad, shallow epeiric sea environment during the Middle Devonian, with the formation's boundaries defined by facies shifts rather than abrupt depositional edges. Subsurface data indicate that the Onondaga may continue southward into under younger strata, but surface exposures in New York are confined to this east-west belt. Facies transitions within the Onondaga are pronounced from west to east, evolving from thick, coarse-grained reefal buildups rich in corals and in western and south-central New York to finer-grained limestones with increased argillaceous content in the east, reflecting a paleogeographic from open-marine, high-energy platforms in the west to quieter, more proximal shelf environments approaching the eastern landmasses, influencing both thickness and lithologic composition. Post-depositional have significantly altered the current exposure patterns of the Onondaga Limestone, with folding and faulting from the Taconic and Alleghenian orogenies creating structural highs and lows that control distribution. The , in particular, contributed to differential uplift and erosion, exposing thicker western sections while eroding thinner eastern equivalents in some areas. These tectonic events, occurring between 400 and 250 million years ago, superimposed on the original depositional geometry, resulting in the fragmented and dipping exposures observed today across the Appalachian Basin.

Paleontological Content

Key Fossil Assemblages

The Onondaga Limestone hosts a diverse Middle Devonian (Eifelian) fossil assemblage dominated by , reflecting its deposition in shallow to deeper subtidal environments across New York, , , and . Key groups include corals, brachiopods, trilobites, and , with additional contributions from bivalves, gastropods, ostracods, and stromatoporoids varying by stratigraphic member and locality. Corals form a prominent component, particularly in the Edgecliff Member, where tabulate forms such as Favosites and Syringopora contribute to bioherms and biostromes, alongside rugose genera like Synaptophyllum, Eridophyllum, Heliophyllum, Siphonophrentis, and Metaxyphrentis prolifica. Brachiopods are ubiquitous and often dominant, with articulate forms including Mucrospirifer mucronatus, Atrypa (e.g., A. reticularis), Schizophoria, Leptaena, Pseudoatrypa, Megakozlowskiella, Chonetes, Pacificocoelia, Paraspirifer acuminatus, Spinocyrtia, Tropidoleptus, Athyris, and Mediospirifer appearing in diverse communities across members like the Nedrow and Moorehouse. Trilobites, though less abundant, include Phacops rana, Odontocephalus, proetids, dalmanitids, and Dipleura, typically in finer-grained facies. Crinoids are widespread, represented by ossicles and crowns of Arachnocrinus, Tripleurocrinus, Schultzicrinus, Edriocrinus, and Haplocrinites, especially in coarse packstones and grainstones. Bivalves such as Nuculites and Cypricardella, gastropods including platyceratids, Palaeozygopleura, and Bembexia, and ostracods occur more frequently in lower members like the Nedrow and Cherry Valley, often as minor elements in wackestones. Stromatoporoids, framework builders in reefal settings, are concentrated in the Edgecliff Member, where they associate with large heads. Biofacies exhibit clear variations tied to depositional depth: shallow, high-energy settings in the Edgecliff Member feature reef-building corals, stromatoporoids, and robust in rudstones and grainstones, while deeper, quieter intervals in the Nedrow, Moorehouse, and Cherry Valley Members yield pelagic trilobites, gastropods, and low-diversity assemblages in micritic limestones and shales. These assemblages transition westward from coral-dominated bioherms in New York to more argillaceous, -rich facies in Ohio equivalents like the Columbus Limestone. Fossils are primarily preserved as calcified shells and skeletons within the matrix, with excellent articulation in aerobic, shallow-water deposits; however, chert replacement (silicification) affects corals and brachiopods in the Edgecliff, while pyritization and phosphatization occur in dysaerobic, deeper basinal beds of the Cherry Valley. Fragmentation is common in high-energy rudstones, but intact crowns and steinkerns are noted in protected settings.

Biostratigraphic Role

The Onondaga Limestone plays a pivotal role in as a marker horizon in the Middle Devonian (Eifelian) sequence of the Appalachian Basin, enabling precise dating and of strata through its distinctive assemblages. Zone fossils, particularly such as Icriodus species, dominate the shallow-water biofacies and define key Eifelian biozones, including the "patulus" zone in the lower formation and the "costatus costatus" zone in the upper parts. Brachiopods complement these, with species like Spinatrypa aspera serving as index fossils that delineate member boundaries, such as between the Edgecliff and Nedrow members, due to their restricted stratigraphic ranges and abundance in specific lithofacies. This formation's biostratigraphic utility extends to regional correlations, where it acts as a reliable marker bed underlying the Marcellus Shale and overlain by the Hamilton Group, facilitating meter-scale matching across New York, , and via shared and assemblages. For instance, the first appearance of dark shales in the LeRoy bed signals the transition to the Hamilton Group, while Tioga Bentonites provide additional tie points to the Marcellus Formation's lower members like Cherry Valley. These biozones align with European Eifelian standards through like Polygnathus linguiformis, enhancing intercontinental ties. In practical applications, the Onondaga Limestone's supports subsurface correlation in oil and gas exploration, particularly for identifying pinnacle reefs and bioherms in the Appalachian Basin subsurface. and zonations guide reservoir characterization and mapping in areas like southern New York, where the formation's thickness variations inform drilling targets and structural interpretations.

Economic and Industrial Uses

Dimension Stone Production

The Onondaga Limestone has been quarried as dimension stone since the mid-19th century, prized for its durability, light gray color upon , and fine-grained texture that allows for precise cutting and . These qualities stem from its dense, semicrystalline structure, primarily composed of 96% with low insoluble residues, enabling applications in structural elements such as foundations, exterior walls, and ornamental features. Early extraction focused on local needs, with the stone's even bedding—typically 2 feet thick—facilitating large block production for building purposes. Principal quarries are located in Jamesville and , where operations began in the 1850s and expanded significantly by the early to supply construction demands in . The Jamesville , for instance, has historically yielded substantial volumes of blocks, though dimension stone output represents a fraction of total production compared to crushed aggregates. Modern quarrying by family-owned operations, such as those established in 1948, continues to emphasize fabrication and installation of Onondaga blocks for veneer and structural use. Quarrying activities at sites like Jamesville have faced controversies, including legal challenges from the Onondaga Nation alleging violations of land rights, environmental of Onondaga Creek, and disturbance of sacred sites. These disputes, part of broader indigenous land claims filed in 2005, have implications for operational sustainability and were upheld in part by an international human rights commission in 2023. Key physical properties enhance its suitability for dimension stone, including a density of approximately 168 pounds per , very low absorption averaging 4.7% by weight, and implied low that contributes to resistance against and freeze-thaw damage. Specimens from New York quarries have demonstrated , remaining in good condition after 1,875 to 1,925 freeze-thaw cycles in testing. The stone's high modulus of elasticity (2,000,000 perpendicular to ) indicates rigidity under load, classifying it among the strongest commercial limestones evaluated for building applications. Notable applications include the Syracuse City Hall, constructed between 1889 and 1893 with Onondaga limestone facades for its solid yet ornamental qualities, and the Syracuse Post Office built in 1887 using blocks from nearby quarries. Additional local examples encompass the Hall of Languages at and various 19th-century public buildings and churches in the Syracuse area, where the stone's fine texture supported detailed architectural features. These uses highlight its role in regional , leveraging proximity to quarries for in heavy construction.

Other Geological Applications

The Onondaga Limestone is widely quarried and crushed for use as aggregate in road bases and construction applications, providing a durable base material for infrastructure development in regions like central New York and southern Ontario. In addition, it served as a key raw material in cement production through historical operations in areas such as Jamesville, New York, where it was processed into Portland cement at facilities with capacities exceeding 900,000 barrels per year as of the mid-20th century. Calcined Onondaga Limestone produces high-quality lime, which is applied in to neutralize acidic soils and enhance crop yields, as well as in processes to adjust pH and remove impurities. Production of lime from this formation historically occurred in the Syracuse area until the early , with modern uses continuing through industrial byproducts in the region. Due to its topography, characterized by solution-widened joints, sinkholes, and disappearing streams, the Onondaga Limestone functions as an important , particularly in eastern , where it supplies municipal and industrial water with well yields averaging 20 gallons per minute. The formation's thickness varies from 25 to 110 feet across its extent, facilitating through enhanced permeability, though over-pumping has led to declines of 20 to 50 feet in water levels since the . The chert nodules within the Onondaga Limestone, particularly from the Clarence member, were a vital resource for prehistoric , who knapped them into tools, projectiles, and other lithics due to their fine texture and properties. This material dominated assemblages at sites in , such as French 3 and Guenther, supporting early reduction sequences and toolmaking traditions dating back to Paleoindian times. Instrumental has confirmed its chemical distinctiveness, enabling studies with up to 85% accuracy in tracing sources along the . In scientific research, samples from the Onondaga Formation are routinely analyzed for geochemical signatures, including carbon (δ¹³C averaging 1.6‰ VPDB), to reconstruct ocean chemistry, organic carbon burial rates, and environmental shifts potentially linked to sea-level fluctuations and diversification. These studies, conducted on outcrops in like Cherry Valley and Cazenovia, integrate data with petrographic evidence to infer paleoecological changes without direct diagenetic overprinting.

Historical and Scientific Context

Discovery and Naming

The Onondaga Limestone was first formally described in 1839 by Lardner Vanuxem during the New York State Geological Survey, which was closely tied to engineering assessments for canal construction in the region. Vanuxem applied the name to the prominent exposures of darker, fossiliferous limestones in Onondaga County, New York, noting their position above the chert-rich "Corniferous Limestone" and their abundance of chonetid brachiopods. These observations highlighted the unit's distinct lithology and stratigraphic value in central New York. In the following year, James Hall expanded on this initial recognition in his reports for the survey's fourth district, designating the Onondaga as a critical marker horizon within the System. Hall's detailed descriptions emphasized its crinoidal composition and consistent layering, which facilitated early correlations across the Appalachian Basin, and he subdivided it into lithologic units that laid the groundwork for later refinements. His work, published in , marked the formation's broader acceptance as a key reference for Devonian stratigraphy in New York and adjacent states. The type locality of the Onondaga Limestone is in , where it displays the formation's typical gray to grayish-blue, compact, crystalline limestone, often weathering to lighter tones and containing abundant fossils. Early surveys encountered confusion with the underlying Helderberg Limestone, as both units share similar calcareous characteristics and proximity across the Silurian-Devonian boundary; this led to overlapping nomenclature in initial mappings. By the 1870s, this stratigraphic ambiguity was resolved through refined paleontological analyses and field mapping, which confirmed the Onondaga's exclusively affinity based on its diagnostic and unconformable relations with older rocks. Concurrently, evolved from the earlier "Onondaga Salt Group"—a broader designation that incorporated associated evaporites and basal limestones—to the focused "Onondaga Limestone" as a standalone formation, reflecting improved understanding of its depositional and temporal isolation.

Stratigraphic Correlations

The Onondaga Limestone correlates laterally with the Detroit River Group in the subsurface of the Michigan Basin, where the dolomitic and evaporitic facies of the Detroit River pass eastward into the more purely carbonate sequences of the Onondaga. In central Kentucky, it is equivalent to the Boyle Dolomite, a cherty, dolomitic limestone unit containing fossils suggestive of the Onondaga fauna, such as brachiopods and corals. Similarly, in southern Indiana and adjacent Kentucky, the Onondaga corresponds to the Jeffersonville Limestone, a medium- to fine-grained, fossiliferous unit with spiriferid brachiopods like Spirifer gregarius marking its lower part. Biostratigraphically, the base of the Onondaga Limestone defines the onset of the Onondaga Fauna in the North American Middle chronology, characterized by diverse coral-stromatoporoid assemblages and such as Polygnathus costatus. This serves as a key marker for regional correlations within the Appalachian and basins. Internationally, the Onondaga Limestone aligns with the Eifelian Stage of the Middle in , particularly the Couvinian substage in , based on shared zones and ammonoid assemblages. Its upper portions approach the Eifelian-Givetian boundary, providing a reference for trans-Atlantic correlations of shallow-marine carbonate platforms. The formation exhibits diachroneity, with basal members deposited earlier in western exposures (overlying older rocks) and progressively younger eastward, reflecting the migration of carbonate belts across the Appalachian foreland during Eifelian transgression.

References

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  44. https://www.jstor.org/stable/30067366
  45. https://pubs.usgs.gov/bul/1180b/report.pdf
  46. https://dam.assets.ohio.gov/image/upload/ohiodnr.gov/documents/geology/RI70_Janssens_1968.pdf
  47. https://pubs.usgs.gov/sim/3006/SIM3006.pdf
  48. https://www.uky.edu/OtherOrgs/KPS/goky/pages/gokych05.htm
  49. https://nysl.ptfs.com/data/Library1/Library1/pdf/1895260.pdf
  50. https://ottohmuller.com/nysga2ge/Files/1994/NYSGA%25201994%2520A4%2520-%2520Stratigraphy%2520and%2520Facies%2520Relationships%2520of%2520the%2520Eifelian%2520Onondaga.pdf
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